STUDIA GEOLOGICA POLONICA

Transkrypt

1 p o L S K A A K A D E M A N A NSTYl:UT NAUK GEOLOGCZNYCH U K STUDA GEOLOGCA POLONCA Vol. LXXXV BUDOWA G E O L O G C Z N A P E N SK E G O SK A Ł K O W E G O P A SA Pod redakcj'ł K. Birkenmajera C zęść V GEOLOGY OF THE PENNY KLPPEN C A R P A T H A N P OL A N D B E L T, Edited bll K. Birkenmajer Part V W A R S Z A W A W Y D A W N C T WA 1986 G E O L O G C Z N E

2 p o L S K A A K A D E M A N A U K N STYTU T N A U K G E O L O G C Z N Y C H STUDA GEO LOGCA POLONCA Vol. LXXXV W A R S Z A W A W Y D A W N C T W A G E O L O G C Z N E

3 REDAKTOR (EDTOR) prof. dr hab. Stefan Zbigniew Różycki członek rzeczywisty PAN SEKRETARZ NAUKOWY (MANAGNG EDTOR) prof. dr inż. Krzysztof Birkenmajer członek korespondent PAN KOMTET REDAKCYJNY (EDTORAL COMMTTEE) pro f. da inż. Krzys zt of Bir kenmajer, ezł. ko resp. PAN prof. dr hab. Ryszard Gradz ińsk i doc. dr hab. Zofia Michalska prof. dr hab. Stefan Zb ig niew Ró ży ck i, czł. rze cz. PAN pr of. dr Jerzy Znosko, czł. koresp. PAN ADRES REDAKCJ (ADDRESS) nstytut Nauk Geo log icznych Po lskiej Akademi i Nauk Praco wnia Tektoniki Karpat, Kraków, Se nacka 3 Redaktor wydawnictwa: Teresa Kasztelan ic Redaktor techniczny: Urszu la Baszyńska Korektor : He le na Kmoch Copyr ight by Wyda wnictwa Geolo gicme, 1986 SBN W Y D A W N C T W A G E O L O G C Z N E W A R S Z A W A 1986 Wydanie. Nakład egz. Format B5. Ark. wyd. 16,0. Ark. druk. 12,1Z5. Oddano do składania Podpisano do druku w kwietniu Druk ukonczono w kwietniu Cena 300. Drukarnia Narodowa Zakład 6, Kraków ul. E. Orzeszkowej 7. Zam. 439/85. P45

4 S T U D A GEO L OG CA P O L O N CA, Vol. LXXXV B U DO W A G E O L O G C Z N A P E N ŃS K E G O P A S A S K A Ł KO W E G O Pod redakcją K. Birkenmajera Część V GEOLOGY OF TH E P EN NY KLPPEN C A R P A T H A N S, P O L A N D B E L T, Edited by K. Birkenmajer Part V W A R S Z A W A W Y D A W N C T W A 1986 G E O L O G C Z N E

5 TR ESC CONTENTS K. B i r k e n m a je r St ages of st ructu ral evo lu tion of the Pien iny Klippen Belt, Ca rpathians. 7 Etapy ro zwo ju st ruktu ra lnego pienińskiego pasa skałkowego (Ka rpaty). St reszczeni e 32 A. J. K rawczyk, T. Słomka Wykształcenie i sedymentac ja fo rmac ji sz lachtowskie j (jura) na wschód od Sz czawnicy (jednostka Gra jcarska, pien iński pas skałko wy) De ve lopment and sedimentation of the Szlachtowa Fo rmation (Ju rassic flysch) east of Szczawnica (G rajca rek Unit, Pieniny Klippe n Be lt, Ca rpathians). Summa ry 129 J. Dudziak Nannoplankton wapienny z fo rmac ji sz lachtowskie j (jura) w potoku Szto lnia, pieniński pas skałkowy Ca lc areous nannop lankton from the Szlachtowa Fo rmation (Jurass ic) of Sztolnia Cłeek. Pieniny Klippen Belt, Ca rpathians. Su mma ry. 141 E. Głuchowski, A. J. K rawczyk, J. Myszkowska, T. Sł omka Litofac je i fauna wapienia krynoidowego ba jos u je dnostki czo rs ztyński ej koło Dursztyna (pieniński pas skałkowy) Lithofacies and fauna of Ba jo cian crinoid lim estone ne ar Du rs ztyn (Czo r sztyn Su ccession, Pieniny Klippen Be lt., Ca rpathians). Summa ry. 154 J. Dudziak St ra tyg rafia fli szu podhala ńskiego (p aleogen) na podstawie nannop lanktonu wapiennego.. Fo rmac je choch ołowska i ost ryska. 157 St ratig raphy of the Podh ale Flysch (Pa laeogene), Cent ral Ca rpathians, based on ca lcareous nannop lankton.. The Chochołów and Ost rysz fo rm ations. Summary. 171

6 ST U D A GEOLOGCA POLO N CA Vol. LXXXV, Warszawa 1986 Budowa geologiczna płentńsktego pasa skatkowego Pod redakcjq K. Blrkenmajera Cz. V K R Z Y S Z TO F B R K E N M AJERl STAGES OF STRUCTURAL EVOLUTON OF THE PENNY KLPPEN BELT, CARPATHANS (Figs 15) Abstract The Pieniny Klippen Bełt represents trace of a major axial suture in the earpathian fold belt, about 600 km long but only from a few hundred metres to about 20 km wideo t is a heterogenous structure eonsisting of the Klippen sueeessions proper and their sedimentary cover, moreover of nner earpathian (Manin etc.) and Outer earpathian (Magura) units ineorporated in the Bełt dur ing its long deformational history. Nim.e ctistincti' e stages of struetural evolution of the Bełt have been distinguished: (A) nitial stage of basin formation as. a result of extensicmal faulting elose to the TniassieJu'assie boundary; (B) nitial expansio'l stage due to oeeanietype rifting and oeeanfloor spreading (TriassieJurassie boun dary a1 d Early Jurassic); (e) Pelagie stage (Jurassie Early eretaeeous) ; (D) nitial eon1pressdon stage (Early eretaceous) rełated to partial subduetion of the Pieniny Klippen Basin under southern Exotie eordillera; (E) Main Late ere taeeous Early Tertiary eompression stage, ineluding three sueeessive de forma llion phases related to subduetion in the central and northern furrows of oceanie basement under the Exome eorddllera (s, hern), respeetively; (F) Palaeogene ex.pansi'on stage ; (G) Early Mioeene (Savian) eompression stage the result of eollision between the European Pl'ate a 1d the Central earpathianpannonian Mioroplate; (H) Early Miocene (late Savian) trans pression stage due to rotation of nner Carpathiall1s respective to Outer earpathians along the Pieniny Klippen Belt, with formation of lcmitudinal strikeslip faults; (J) Mid Mioeene (Styfi.a1) eompression stage expressed in the Belt as transversal strikeslip faults. NTRODueTON The Pieniny Klippen Bełt represents trace of a maj or axial suture in the Carpathian fod belt, about 600 km long bu only from a few hundred metres to about 20 km wideo t separates two major structural units: the nner Carpathrians to the SlQuth, and the Outer Carpathians to nstitute of Geological Sciences of the Polish Academy of Sciences, Tectonics Laboratory, ul. Senacka 3, Kraków.! Manuscript received October 30, Research Project MR..16 of the Polish Academy of Sciences.

7 8 KRZYSZTOF BlRKENMAJER the north (Fig. 1). n its present form, the Pieniny Kl:ippen Belt is a heterogenous structure oonsisting of the Klippen successions proper deposited in the Pieniny Klippen Basin, and their sedimentary cover, moreover of the nner Carpathian and Outer Carpathian elements in corporated in the Belt during the Late Cretaceous Early Palaeogene, and Early Neogene folding. The Pieniny Klippen Belt is bounded in the south and north along most of its length by strikeslip faults of Early Miocene age. t has long been known that these vertical to subvertical faults (see Birkenrnajer, 1 960, 1 974; Birkenmajer et al., 1 979) represent fractures of major impor tance in the structure of the Carpathian fold belt but thetir strikeslip character has only recently been recognized (Birkenmajer, 1981, 1 983, GORy S SWP O KRZYSKE y ;/ 12 o c:::=j li! l' :15 E72J ===J=1 _ / =k" f7z1 < :: == = 1 :::: _ : 3 _ 4 [ 3 7 B 11 / , /:;. ls 200km : : : : :1 10 Fig. l Main structural e1ements of the Carpathian orogen. nterpreted from Mahel' et al. (1974) and Sandulescu (1980b) l Outer Plates: northern Foreland ot the CarpathJan orogen (European Platform) and Moesian Platform; 2 Foredeep (Neogene molasse), outer zone; 3 Foredeep (Neogene molasse), inner zone; 47 Fold belt; 4 Outer zone (major flysch trenches); 5 Central East CarpathJan Massft (nner Dacldes) and assoclated MldCretaceous nappes (Outer Da cides), and equivalent zones in the South Carpathians and Dinarides (outer zone); 6 Pieniny Klippen Belt; 7 nner unts (nterndes); B nterarc postnappe cover (Palaeo gene, partly Late Cretaceous); 9 are ot calcalkaline Neogene volcanics ; 10 Neogene molasse in intramontane (ntraarc) basins; 11 selected taults and flexures; 12 strlkesllp proven; 13 strikeslip supposed; 14 Odra Fault basalts; 15 Pieniny Mts andesites

8 STAGES OF STRUCTURAL EVOLUTON OF TRE PENNY a). The northern boundary fault zone is a leftateral strikeslip fault. and the same seems to be true of the southern boundary fault. The Belt was a megashear zone of translation durdng early Neogene clockwise rotation of nner Carpathians respective to Outer Carpathians. The strike slip translation caused megabreccia1lion and megaboudinage so characteristic of the Klippen Belt structure. Four epochs of structural deformation have contributed to the present structure of the Pieniny Klippen Belt: () The Early Cretaceous subduetion of oceanic crust under Exotic Cordi11era (in the south) considerably redueed the width of the Pieniny Klippen Basin; () The Late Cretaceous Early Palaeogene subduetion of oceanie crust segments, central and northern, under the Exotic Cordillera and the Czorsztyn Ridge, respectively, produced during three suecessive stages of folding (late Subhercynian and two Laramian phases): (1) northvergent nappes; (2) refolding of nappes together with synorogenie molasse and flysch; (3) retroarc thrusting along the northern margin of the fom belt; () The Early Miocene (Savian) deformation resulting from continentoontinent typ e collision between the European Plate and the Central CarpathianPannonian Mieroplate, caused fragmentation of older nappes and their autochthonous substratum (Czorsztyn autochthone), moreover faulting and retroarc thrusting, in the successon; (V) Megabreceiation and megaboudinage of the Pieniny Klippen Belt began to form at stage () but eontinued along with longitudinal and, subsequently, transversal strikeslip faulting as long as MidMioeene (late SaVlian and Styrian phases). The Pieniny Klippen Belt suture eorresponds to a major structural break between\ the nner and Outer Carpathians (see Figs 2, 3). This is also evidenced by deep seismic sounding (e.g., SoLogub et al., 1973; Uehman, 1973; Ney, 1975) whieh shows that the Mohorovicić (Moho) diseontinuity drops there abruptly by about 15 km down ta about 50 km below the surface northward of the Belt. This hs be en interpreted in terms of a palaeosubduction zone whieh had been active mainly during Late Cretaeeous tlimes,. and remobilized during Early Palaeogene (Laramian) and Neogene (Savian and Styrian) folding, with aftereffeets as young as MidLate Mioeene through Pliocene and even Pleistocene times (Birkenmajer, 1976, 1977b, 1978). Along most of its length, from Rumania (P,oiana Botizei) in the east, through Transcarpathian Ukraine (USSR), Eastern Slovakia, Poland, and Western Slovakia. the Piieniny Klippen Belt follows the innermost Out er Carpathian nappe the Magura Nappe. The southernmost part of this nappe is rooted in the Pieniny Klippen Belt. The Bełt temporarily disap pears from the surface under thick Late Tertiary molasse of the Vienna Basin (see, e.g., Jiżicek & Tomek, 1981), and reappears near V:iJenna as part of the Laab Nappe (Prey, 1965), equivalent of a part of the Magura Nappe, eventually plunging tpgether with the Laab Nappe under the Limestone Alps. The Grestener Klippenzone in front of the Laab Nappe, and in Voralpen, belongs to another, more outward zone, comparable W1ith the Silesian and Subsilesian zones in the Carpathians (Prey, 1960, 1965; Birkenmajer, 1961).

9 10 KRZYSZTOF BRKENMAJER N P lenlny KLPPEN s NOWY TARG DEPRESSON BELT PODHALE DEPRESSON Bońsl4J o O : km 5 km Fig. 2 Geological crosssection of the Pieniny Kippen Bełt along the Kraków Zakopane geotraverse (Birkenmajer, 1985b, c) M a g u r a N a p p e: Mi Jurassie to Albian; Mc Cenornanlan to Maastrichtian; Mp Palaeogene. P i e n n y K l i P P e n B e l t: G Grajcarek Unit (Laramlan Magura unit: Mi + MC); C Czorsztyn Unit (Jurassie and Lower Cretaceous) ; CC incornpetent Upper Cretaceous rnarls and flyschoid rocks. Czorsztyn and transltional (?) unlts; B Branisko Nappe; P Pieniny Nappe;, i Maastrichtlan rnolasse and flysch (Jarrnuta Formation); MS Maruszyna Sca1e. P o d h a l e P a l a e o g e n e (Central Carpathians): n basal conglomerate and nummulitle llrnestone. Lararnian overthrusts n the Pieniny Kllppen Belt barbed ; Tertlary faults rnarked by heavy lnes and dashes; deep boreholes rnarked at Bańska and Maruszyna STRUCTURAL UNTS AND THER PALNSP ASTCPALAEOTECTONC SETTNG The following structural units may be distinguished in the Pieniny Klippen Bełt: (A) Klippen successions (occasionally Triassic, but mainly Early Jurassic through Campanian, metimes up to Early Maastrichtlian). They formed in a separate basin the Pieniny Klippen Basin between two r.i:dges: the Czorsztyn Ridge in the north, and the Exotic Ridge in the south (Fig. 5);

10 STAGES OF STRUCTURAL EVOLUTON OF THE PENNY (B) nner Carpathian successions ( Early Jurassic through Turo rui an) formed in a basin situated to the south of the Exotic Ridge: Manin Basin sensu lato, in possible continuation with the Hightatric mne (ridge) ; (C) Myjava successions (Late Cretaceous an d Early Palaeogene), lin their Late Cretaceous parts equlivalents to the Gosau facies. These units postdate midcretaceous folding in the Hightatric (sensu lato) and Sub tatric zones. The Late Cretaceous Myjava basin was in forearc position with respect to midcretlaceous fold belt of nner Carpathians; the Early Pala,eogene Myjava basin formed in a backarc setting, with respect to Laramian Pierui.ny fold belt; (D) Jarmuta cover (Maastrichtian): freshwater and marine molasse and flysch deposited upon late Subhercynian tectonic Klippen units (nappes and a utochtlrone), in intraarc setting. The cover was then partly refol ded together with some nappes during Laramian phases in the Pieniny fold belt, and in the Magura Trough to the north of [t (in forearc set ting); (E) Outer Carpathian succession: MidJurassic thmugh Maastrichbian elements of the innermost part of the Magura Trough, incorporated as the Grajcarek Unit in the Klippen Belt duni.ng latelaramian fol dingo This succession includes oorearc flysch wedge of the Jarmuta co ver; (F) Palaeogene cover (Paleocene through Oligocene) unoonformable upon (A), through (E), of either Magura (Outer Carpathian) or Podhale Sul'ov (Central Carpathian) types. (A) ; K li PPen Successions The Klippen successions include marine sediments laid down in a se parate basin of the Carpathian Tethyan realm, following fragmentatijon by extensional Early Cimmerian faulting (at the TriassicJurassi.c boun dary) of the Triassic carbonate platform. The pretriassic basement is known only from fragments contained as secondary deposit in MidJu rassic sediments. The Triassic platform deposits may some1limes be found as slivers of carbonates at the base of JurassicCretaceous klippes: Hali govce Succession which formed close to the southern margin of the Klippen Basin. Recycled fragments of Early Triassic (Werfenian) clastics, MidLate Triassi.c dolostones and limestones, and LateTriassic (Keuper) shales occur in MidJurassic offshore, often deepwater marine sediments, growing coarser and more frequent northward, in the direction of the Czorsztyn Ridge. They indicate that splinters of Triassic carbonate plat form with their crystalline substratum, ni.mmed the Pieniny Klippen Basin during the Jurassie both from the south and the n orth (Fig. 5). The estimated width of the Pieniny K1ippen BaSin was oj the order of a minimum km during the Callovian expansion stage (Birken maj er, 1 977a, 1 985b). Much more width would be added if we accepted an ocearuictype crust under the central part of the futow. Three main seddmentary zon es may be distinguished within the Pie niny Klippen Basin : (1) the northern ridge and its slope (Czorsztyn Rid ge) ; (2) the central futow; and (3) the southern ridge and its slope (Exo tic Ridge) see Figure 5.

11 12 KRZYSZTOF BRKENMAJER Northern (Czorsztyn) Riige The northern nidge, resp. Czorsztyn Ridge, and its oouthern slope, are represented by sedimentary Czorsztyn Sueeession (oeeasionally Triassie?; usually Early Jurassie through Lower Maastriehtian), developed prineipally as hemipelagie to pelagie organogenie earbonate sediments of medium depth. The Czorsztyn Ridge was an aseismietype ridge a splinter of European Platform separated from it by extensional faulting (close to the TriassieJurassie boundary), and subsequent oceaniefloar spreading and oceanicrift reloea1lion during the Early Jurassie times. Condensed ealeareous deposition Wlith numerous break s eaused by submarine disturbanees of sediments related to MidJurassie (MeooCimmerian) and La1eJurassie to Early Cretaeeous (NeoCimmerian) faulting, and deepsea eurrents, are typical of the Czorsztyn Ridge (Biirkenmaj er, 1958b, 1963, 1975; MiSik, 1979, 1984). Abundanee and dó.versity of invertebrate fossils preserved in the limestones indieate that the Czorsztyn Ridge was a major upwelling zone whieh separated the nner and the Outer North Tethyan (Carpathian) oceanie realms during the Jurassie. The ridge remained submerged during the whole, or most of, its Mesozoie history prior to Late Cretaeeous uplift. t was only slightly disturbed by folding and faulting during the Late Cretaeeous orogeny but remained in its autochthonous position with respeet to the Late Cretaeeous nappes. The Mesozoie sediments of the Czorsztyn Ridge were torn off their erystalline and earbonate (Triassie) basement, strongly breeeiated, megaboudinaged and folded for the first 1lime as late as the Savian orogeny. Competent Jurassie limestones of the Czorsztyn Suecession are usually separated as tectonie klippes from the underlying and overlying marly shaly rocks of this sueeession. The limestones disednformably pieree through steeply dipping to ver1lieal, strongly folded ineompetent marls, shales and flyseh rocks of mainly Upper Cretaeeous age (Biirkenmajer, 1959a, 1963). The presenee Of the Czorsztyn Sueeession is diagnostie for the Pieniny Klippen Belt (Birkenmajer, 1963). This sueeession has no close equivalents in sedimentary sueeessions of other ridges in the Carpatruan realm, though some formations may be common to several of them. The Czorsztyn Ridge may be traeed for most of the Pieniny Klippen Belt length; from the vicinity Of Vienna (Ober St. Veit and Lainzer Tiergarten see Janosehek et al., 1956; Birkenmajer, 1962, 1963) through Western Slovakia, Poland, Eastern Slovakia, to Transcarpathlan Ukraine inclusively (e.g., Uhlig, 1890; Andrusov, 1938, 1953, 19645, 1968; Birkenmajer, 1953, 1963, 1965, 1977a; Alexandrowiez et al., 1968b; Kruglov, 1974; Seheibner, 1968a). t is missing at the easternmost termination of the Pieniny Klippen Belt in Rumania (at Poiana Botizei see Siłnduleseu et al., 1981; Bombita & Savu, 1985). The eharaeter of sedimentation lon the northern slope of the Czorsztyn Ridge is poorly known. Some sed.imentary features of the adjaeent Mid Jurassie through Early Cretaeeous Magura Trough deposits may be nnterpreted in favour of the proximity of the Czorsztyn Rlidge and its northern slope. Sedimentologieal analysis Of black flyseh sediments of Aalenian age

12 m N Q.. W W o W er O LL Ī > C..!:! o Cio O SS ' C) N U O Ol O :R 4! CAR PATHANS s O N o R 1 H Geological crosssection along the!;tructure belo w Magura Nappe, Pieniny Klippen Belt, 1 Marine Miocene cover (moiasse) oi.rian and Precambrian; Mesozoic vertically shaded) ; 3 _ ntramontane freshwater moiasse (Mio it; Mk Krynica Subunit; Mo Orava Subunlt); S _ Grajcarek Unit (Jurassic and Cretaceous ;M J Grybów Unit); 7 Silesian Nappe (S _ lower subunit; S2 upper subunit); 8 Subsilesian Nin molasse not marked); 10 southern periklippen zon e (MA Manin and reiated units; MY e at base (N); 12 Hightatric units (crystalllne core marked by crosses; HT autochthonous COVE iaults; 14 _ minor overthrusts; S _ major overthrusts

13 N O m 1000,: l O UTER ' a.. w W o >. W c (r.!2 o '50 LL o N G A M t!) N u... o N,::. o N A R c "iie o ot; 'JlD "" MS2 Mr \ :. P A E P l o.d "O o '.0 o,6 Mb " NNER D..!!: o o c :J.D c:s U '.2 'c o Ol.. CAR P A T H AN S Mo Mk B ol ' N Gl \ "" :Jt!) ot Pi ' "" t!) PODHALE PAlAEOGENE CAR PATHANS TATRA o V 'c Cl D G EJl 83 j,.!.:1;?.14 EJ K 2 rn D.;r,:,, : l>,. O Slcm S 6 07 s:.,..j 8 lokm 9!fi C Pi 1O M P.P N 'c: "( LlPTOV DEPRESSON m l', \ _ / EUROPEAN 1 1 _i:.a..a....j /....Ji'... Y... ;?':: HT / /Y,... / /;t + R 1 H N o MTS S o ' 5 1 \ EUg. 3 Geological crosssection along the geotraverse Kraków Zakopane ('after.birkenmajer 1985c ; Outer Carpathian part based main1y on Sikorą, 1980; deep structure below Magura Nappe, Pieniny Klippen Bełt, and reation to Central Oarpathian block new interpretation) 1 Marine Miocene cover (molasse) ot European Platform (Foredeep); 2 Platform under the Carpathians (P Permian; K Carboniferous; D Devonia n ; C Cambrian and Precambrian; Mesozoic vertlcally shaded); 3 ntramontane freshwater molasse (M.ioPliocene); 4 Magura Nappe (Cretaceous strata stippled; MS, Ms. Siary Subunit; MT Ra/!a subunit; Mb Bystrica Subunit; Mk Krynica Subunlt; Mo Orava Subunlt); S Grajcarek Unit (Jurassie and Cretaceous elements of the southern margin of the Magura basin ) ; 6 Submagura Nappe units (SM Mszana Unit; SM ObidowaSłopnlce Unit; SM Gry bó w Unit); 7 Sllesian Nappe (S lower subunit; 3. 8 upper subunlt); B Sub ilesian _ (MA Manin and related unlts; s 2 by crosses; HT autochthonous Nappe; 9 Pieniny Kllppen Belt ( C Czorsztyn Unit; CC transitional units; B Branisko Nappe ; Pi Pieninv. M Y Myjava Furrow sedim'ents Maruszyna Scale ) ; 11 _ Podhale Palaeogene flysch (PP) with nummulitic limeotone and conglomerate at base (N); 12 Hightatric unlts (crystalline core marked cover and thrustfolds), and Subtatric nappes (STc Cho/! Nappe; STk _ Krizna Nappe; ST_J oartial units ot the Krizna Nappe) ; 13 fauts; 14 minor overthrusts; S _ major overthrusts

14 STAGES OF STRUCTURAL EVOLUTON OF THE PENNY (Szlachtowa Formation) of the Magura (Grajcarek) Unit indicates (Kraw czyk & Słomka, 1986) that one of the two clastic sources for this flysch wedge coincided with the Czorsztyn Ridge. The source rocks were re presented mainly by carbonates, limestones and dolostones (probably Mid Triassic), and clastics (sandstones, siltstones, claystones: Early Triassic and Carboniferous?), subordinately by plutonie and metamorphic rocks of the basement. Central Furrow The central furrow of the Bienrl.ny Klippen Basin was the site of the deepest, hemipelagic to pelagie, sedimentation, with an abyssal stage of radiolaria chert deposition during MidLate Jurassie times. The southern most part of the furrow was occupied by the Pieniny Succession, the mo re northern part by slightly shallower BraniskQ Succession (in the east) and its lateral equivalents the Kysuca Successi:on and the NiZna Succession (in the west). The Pieniny Succession has been recognized both in the Slovak and Polish sectors of the Belt, between the Orava River Valley in the west, and the Pieniny Mountains in the east. t QCcurs close to the southern boundary faułt of the Bełt, and represents the highest of the Late Creta ceous nappes (Orava River Valley in SQvakia, area west of Szaflary in PQland) lor a kind of higher digitatilon of the BraniskoPieniny Nappe in the Pieniny Mountains. The KysucaBranisko Succession is almost as widespread as the Czorsz tyn Succession. t appears for the first time in the west in the vicinity Qf Vienna (see Birkenmajer, 1962), and soon becomes the most important tectonic unit ią the West Slovak, Polish and East Slovak sectors, reaching as far east as the Transcarpathian Ukraine (USSR). The Pieniny and KysucaBranisko successions are missing from the Rumanian termination of the Belt at Poiana Botizei a. Further north, in the transitiqn zone between the central furrow and the northern ridge (Czorsztyn Ridge), a number Of transitional successions of restricted regional significance developed: the Czertezik and Niedzica successions (in the Polish and Slovak sectors), the Pruske and the Podbiel ( Orava Succession sensu Hasko & Polak, 1978) successions in West Slovakia. The NiZna Succession (Scheibner, 1967) is a variety of the Kysuca Succession deve10ped closer to the southern ridge (Exotic Ridge), probably replacing the Pieniny Succession in parts of West Slovakia. The Liassic through Lower Campanian 4 sediments of the central furrow have been completely torn ou their basement during La te C retaceous nappe thrusting. Thus there is no direct evidence for the character of the basement. t could have been represented partly by attenuated continental crust with thin Triassic cover, and partly (more southward) by an oceanictype crust, especially in the zone of the = a The succession at Poiana Botizei, attributed to the Pieniny Succession by Rumanian geologists (Sfmdulescu et al., 1981; Bombita & Savu, 1985) corresponds better to the Grajcarek (Magura) Succession (Birkenmajer, 1985b). 4 Liassic through Maastrichtian in the Kysuca Succession of West Slovakia (see Hasko & Polak, 1978).

15 14 KRZYSZTOF BRKENMAJER deepest facies (Bositra shales, radiolarites). However no ophiolites have so far been found associated with radiolarites in the Pieniny and Branisko nappes. The hypothetic Oceanic crust in the central furrow could have been of Early Jurassie (Early Liassic) or even Late Triassic age. t would belong to the same zon e as the main oceanie crost domain 'Of the East Carpathians, as known maiinly from obductlion nappes (Transylvanian nappes see Sandulescu & RussoSandulescu, 1979; Sandulescu et al., 1981). Southern (Andrusov) Ridge The southern ridge which separated the Pieniny Klippen Basin from the Hightatric domain sensu lato (Klape Manin Kostelec unitsl), has long been known as the main source of exotic rocks supplied to the Late Cretaceous flysch and conglomerates, partly also to Palaeogene flysch cover Of the Pieniny Klippen Belt and its limmediate vicinity (e.g., Matejka & Andrusov, 1931; Zoubek, 1931; Androsov, 1938, 1953; Birkenmaj er, 1958a, 1960: Birkenmajer & Lefeld, 1969; Wieser, 1958; Marschalko et al., 1976; Misik et al., 1977; Marschalko, 1978, 1979; Misik & Sykora, 1981, and others). There is no unanimous!y accepted name for the southern ridge in question. Such terms as " Exotic Ridge" resp. Southern Exotic Ridge" stress exotic character of its rocks ; the Pieniny Ridge " as used maim"y in older papers, is a misleading term, as the Pieniny Succession is not of a ridge but of a furrow character; " the " Klape Ridge " (e.g., Mahe!', 1981; Saaj, 1982) restricts the sense of the southern exotic ridge to the Klape Succession; other names" such as the "UltraPieniny" vel "UltraPieninic", vel " UtraPienidic" ridge, are too close in spelling and sound to avoid confusion with Penninie elements of the Eastern Alps. My proposal is to :i.ntroduce a new name of the southern ridge in question, namely the Andrusov Ridge in honour Of the late Professor Dimitrij Andrusov who had devoted many decades of ms b'1illiant geological work in the Carpathians to elucidate the composition and the role of this ridge in sedimentary and structural evolutipn of the Carpathians, and the Pieniny Klippen Belt in partrlcular. The petrographic inventory of the sodefined Andrusov Ridge includes Palaeozoic crystalline limestones, metagreywackes and conglomerates, and a variety of Triassic and Jurassie rocks, generally similar to those of the Pieniny Klippen Belt and nner Carpathian units, but with evidently mare shallow development in Upper Jurassie and Lower Cretaceous (e.g., lack of Jurassic radiolarites; appearance of oolitic limes ton es in Upper Jurassie; appearance of reefal Urgonian facies in BarremianAptian). The Urgonian limes ton es seem to be the youngest element of the Andrusov Ridge succession. There is, moroover, a variety of igneous rocks attributed to the Andrusov Ridge, including spilitickeratophyrealbitophyre and rhyolitedacite and andesite volcanics and granitoids. A part of these igneous rocks could be of pretriassic age, but a substantial part is of Early Cretaceous age as shown by KAr dating: M (Marschalko et al., 1976) and Ma (Rybar & Kantor fide MiSik & Sykora, 1981), and correctly assumed already by Wieser (1958). Detrital chromian and ferric

16 STAGES OF STRUCTURAL EVOLUTON OF THE PENNY spineis recognized in the Barremian through Cenomanian sediments of the Klape and Manin successions, moreover chromite, spinel and serpentinite fragments extracted frem exotic BarremianAptian ldmestone pebbles of the Upper Cretaceous " Dpohlav" conglomerates of the Pieniny Klippen Belt of West Slovakia, are considered to be evidences for ultramafic rocks from obducted oceanic crust, probably associated with the discussed ridge (Misik, 1978; MiSik et al., 1980; Misik & Sykora, 1981). Traces of blueschist (hpt) metamorphism recognized in detl1ital materia l (glaucophane, chloritoid) derived from this ridge have been dated on glaucophane schist fragments as 138 and 140 Ma (Rybar & Kantor fide Misik & Sykora, 1981). They mark the beginning of subduction associated with the Andrusov Ridge and transformation of sofar passive ridge into active cordillera (Andrusov Corclillera) as early as the JurassicCretaceous boundary (Figs 4, 5). The nlorthern slope of the Andrusov Ridge was probably occupied by the Haligovce Succession (Fig. 5). This succession starts with Triassic carbonates at the base unconformably overlajin by Liassic marine strata (Horwitz & Rabowski, 1929; Kotański, 1963), followed by MidUpper Jurassic and Lower Cretaceous marine strata (Birkenmajer, 1959b, 1977a) resembling those of the transitional successoons (the Czertezik Succession in particular). The appearance of Urgoniantype limestones (Barremian Aptian) ldnks the Haligovce Succession with the Nizna Succession, and across the Andrusov Ridge with the KlapeManin Basin (Manin Basin sensu lato) where the Urgonian limestones are a widespread facies. Late Cretacoous Globotruncana marls (Jaworki Marl Formation) and flysch deposits (Sromowce Formation) of the Haligovce Succession would also confirm its palinspastic position within the Pieniny Klippen Basin rather than the KlapeManin Basin. On the other hand, the presence of Myjava type Palaeogene (see below) at Haligovce, suggests a close relation with the lauer basin. The southern slope of the Andrusov Ridge oorrelates more or less with the Klape Succession (see below). (B) n n e r C a r p a t h i a n S u c c e s s i o n s Here belong units inclorporated in the PienJiny Klippen Belt most probably during Laramian folding: the Klape Successilon (Unit, Nappe), the Manin Succession (Nappe), and the Kostelec Succession (Unit) (e.g., Andrusov, 1938, 19645, 1968; Mahel', Buday et al., 1968; Mahel' et al., 1974; Began & Salaj, 1978; Marschalko & Kysela, 1980; Salaj, 1982, Kysela, 1984; Rakus, 1984; Michalik Vaśicek, 1984). Generally, they represent a ridgetype (Hightatric) development characterized, i.a., by crin<jdd limestones in the Liassic and Dogger, calcareous organodetrital sedimenta tion during Malm and Lower Neocomian, and a typical Urgonian organogenic calcareous development at the close of Lower Cretaceous. Olistolite beds with Urgond.an blocks (Aptian) and AlbianCenomanian (up to Lower Turonian) flysch beds often very rich in exotic boulders, are indicative of tectonic activity and emergence within the Andrusov Ridge (Cordille. ra) which bordered the basin from the north (Fig. 5). The Klape SuccesslOn might have formed already at the southern slope of the Andrusov Ridge.

17 16 KR ZYSZTOF BffiKENMA.JER Basic effusives in f.orm of submarine flows were associated with faulting and sedimentary hiatuses close to the AptianAlbian boundary (Austrian Phase). n more shallow development in the north (Klape Succession) and in the south (Kostelec Succession) there are numerous sedimentary breaks in the Jurassie through Albian column. n the deeper Manin development, Oxrordian radiolarites (radiolaria cherts) appear locally (at Butkov). Ho wever, the overall Jurassie through Lower C retacoous sedimentary co lumn of the Manm Basin sensu lato (KlapeManinKostelec) is of the ridge and not of the furrow character, corresponding to a shallow to moderately deep marine basin developed on attenuated oontinental crust basement (see Fig. 5). Following Austrian Phase disturoonce (uplift, par tial emersion, basic volcanism related to submarine faułting), a flysch wedge and olistostrome sedimentation appeared suggesting deeperwater sedimentation at the close of the sedimentary cyc le (Albian through Lower Turonian). (C) MYjava Successio ns The sedimentary successions of the Manin Basin (s.l.) were probably slightly folded during MidCretaceous times, and the Turonian hiatus as marked by Marschalko and Kysela ( 1 980, Fig.. 2) may thus correspond to the Meddterranian Phase ; this is however, not a unanimous view (e.g., Began & Salaj, 1978; Salaj, 1 982). There follows the ConiacianSantonian through Maastrichtian successijon of conglomerates, marls, shales and flyschoid rocks of Gosau facies, considered by some authors (op. cit.) to be continuous across the CretaceousTertiary boundary. The facial deve lopment of the Late Cretaceous sediments is here generally referred to as the Myjava facies (Andrusov's term, 1 965) or Myjava Furrow (sensu Scheibner, 1 968b, Fig. 2; but not Salaj, 1 982, Fig. 3, whose " Myjava Stretch" covers the Pieniny Klippen Bełt proper, and not the KlapeManin zones), or " periklippen CretaceousPalaeogene" (Andrusov & Samuel, 1 973; Mahel', 1 982). The overall analysis points to folding of the KlapeManinKostelec zone together with its Late Cretaceous Myjava cover during the Lara mian orogeny (e.g., Marschalko & Kysela, 1 980; Mahel', 1 982), and at least partial thrusting of these units over the Andrusov Ridge and the already folded Pieniny Klippen Bełt accreted to it from the north (Fig. 5). The hiatus at the base of Palaeogene, as accepted by Salaj (1982) for the Klape Successi.on, could be a phenomenon characteristic for the Andrusov Ridge and the Pieniny Klippen Bełt accreted to it from the north, as well as for some zones of the Myjava Furrow adjacent to the Andrusov Ridge from the sauth, the latter characterized by MidLate Paleocene reef complexes (Scheibner, 1 968b; Andrusov, 1 969). The equivalents to the Myjava successions are poorly represented in the area to the east of the River Vśh Valley. n the Dunajec River Valley, there appears a very narrow, discontinuous, strongly folded zone along the sauthern border of the Klippen Belt (at the c'ontact with the Podhale Palaeogene flysch), distinguished as the Maruszyna Scale. This zone consists of pelagic, seemingly continuous deposits of Late Creta

18 STAGES OF STRUCTURAL EVOLUTON OF THE PENNY ceous and Early Palaeogene age, of characteristicaly smal thickness. The Upper Santonian through Upper Maastrichtian marls and marly shales rich in globotruncanids, with subordinate sandstlone intercalations, are folowed by PaleoceneEocene variegated shales and marls with globorotaliids (Alexandrowicz & Birkenmajer, 1978; Jednorowska, 1980; Birkenmajer & Jednorowska, 1983). The substratum of these sediments is unknown: they may have formed lon a submerged ridge above c.c.d., probably on a part of the southern, unfolded slope of the Andrusov Ridge (Cordillera ). The l1orthern margin of the Myjava Furrow is recognizable at Haligovce (pieniny Mts) where the Haligovce Succession is unconformably covered by basal Palaeogene conglomerates with coral and forarruiniferal limestone intercalations (Middle and Late Eocene). They pass southward in to marlstones and claystones with subordinate limestone intercalations containing earliest Paleocene through Late Eocene foraminifers (Horwitz & Rabowski, 1929; Matc jka, 1961; Scheibner, 1968b). (D) Jar m u t a C o v e r The Maastrichto.an clastic cover (Klippen mantle) developed as fresh wat er and marine molasse (conglomerates with exlotic and loeal material), and sandy flyseh of the Jarmuta f'acies (Jarmuta presents intraare and forearc settings with respect to the late Subhercynian Laramian Ptieniny fold belt. t unconformably covers prelaramian tectonic units consisting of the Klippen successions and is, moreover, incorporated in Laramian structures of the Belt. Wildflysch (oliistostrome) and sandy flysch of the Jarmuta facies were deposited partly simultaneously with Laramian thrusting within the Belt (intraarc setting) and to the north of the fold belt dn the Magura Trough (forearc setting). (E) O u t e r C a r p a t h i a n (M a g u r a) S u c c e s s i o n This is a Mesozoic succession (MidJurassic through Maastrichtian) formed in rather deep oceanie trough northward of the Czorsztyn Ridge (Birkenmajer, 1965, 1970, 1977a). t was incorporated in the Pieniny Klippen Bełt as a result of Laramian retroar c folding and thrusting (Fig. 5 Grajcarek Unit). The succession begins with black flysch of?toarcian' to Aalenian age, the oldest turbidite deposition known from the Carpathians. There follows deepwater condensed sedimentation, in the succession, of: shales, marls, radiolaria cherts (radiiolarites) and limestones (Bajocian through Lower Cretaceous), very similar in facies and sequence to the Branisko and Pieniny successions, but markedly differing in thickness which is smalest in the Grajcarek Undt. There is a distinct change in typ e of sedimentation about the Lower Upper Cretaceous boundary: contrary to the Pieniny Klippen Basin where planktonrich Globotruncana marl and flysch facies (Jaworki and Sromowce formations) are characteristic, vamegated planktonpoor deep wat er shales with arenaceous foraminifera (Albian through Campanian) 2 Studia Geol. Pol. vol. 88

19 18 KRZYSZTOF BRKENMAJER are typical of the Magura Trough. Radiolariabearing shales are connected with characteristic anoxic zones horirons in the Albian and uppermost Cenomanal1 lowermost Turonian of both the Klippen Basin and the Magura Trough, however true radiolarites up to several metres thick appear in the Albian of the Magura Trough Only. The Grajcarek (southern Magura) sedimentary one was slightly tectonically disturbed about the CampanianMaastrichtian boundary in the vicinity of the Czorsztyn Ridge. As a resułt, the upper part of the variegated shales (Malinowa Shale Formation) is often eroded, and fragments of Jurassic and Cretaceous rocks of the Magura Trough appear as secondary deposit in conglomerates and breccias of the succeeding Jarmuta Formation (Maastrichtian). Another folding in this zone, resulting in retroarc thrusting of the Magura Trough sediments (Grajcarek Unit) over the late SubhercynianLaramian units of the Klippen Belt, took place during Paleocene (late Laramian phase). Both tectonic disturbances we re related to subduction of oceanic crust segment of the Magura Trough under the Czorsztyn Ridge (Fig. 5). The Grajcarek Unit is well recognizable in the Polish and East Slovak sectors of the Piieniny Klippen Belt, less so in the West Slovak sector. ts eastern termination is at Poiana Botizei in Rumanda (Birkenmajer, 1985b). (F) P a l a e o g e n e C o v e r The Palaeogene cover of the Pieniny Klippen Bełt is mainly of the Maguratype flysch character. t forms a normal sedimentary cover unoonformable upon Laramian tectonic units of the Bełt. The Magura Nappe (innermost flysch nappe of the Outer Carpathians) is rooted in its southernmost part within the Pieniny Klippen Belt. The Palaeogene cover of the Myjavatype occurs disconformably and discontinuously along the southern margin of the Pieniny Klippen Belt, from West Slovakia (the widest areas of exposure) through Poland and East Slovakia, probably as far east as Transcarpathian Ukraine and Rumanian Carpathians. Thds cover is usually in tectonic contact with the Podhale Flysch (Upper Eocene Lower Oligocen e) and its basal conglomerates (Sul'ov type) and organogenic limestones (nummulitic, reefal) of MiddleUpper Eocene age. The basal conglomerates, together with their substratum (e.g., Haligovce Unit, Pieniny Mts) are sometimes incorporated into the Klippen Belt and acquire dts Neogene tectonic style. The Neogene and Quaternary sedimentary covers are unconformable upon older units of the Pieniny Klippen Belt. Though often disturbed by young faułting, sometimes also folding, these sediments never acquire tectonic characteristies and style of the Pieniny Klippen Belt uruits. They are postorogenie with respeet to the Savian orogeny. The Miocene volcanics (mainly andesite dykes and sills) of the Pieniny Mountains area, are intrieately related to the latest stages of teetonie deformatlion in the Pieniny Klippen Bełt. They are always post teetonie with respect to the main Neogene (Savian) phase of folding,

20 STAGES OF STRUCTURAL EVOLUTON OF THE PENNY while being either preteetonie o r postteetonie with respect to the Mid Miocene (Badenian) Styrian phase folding. MESOZOC TRANSFORMFA UL T OC EANCRF T PATTERN The present, strongly arcuate shape of the Carpathian fold belt, an example of looparc, is a postcretaceous tectonic feature. There is palaeo magnetic evidence that the curvature of the Pieniny Klippen Belt, and the Carpathian arc as well, are the result of postcretaeeous rotation (e.g., Ba.Zenov et al., 1981). Prior to Late Cretaceous times, the Pieniny Klippen Basin, and the whole West Carpathian geosynelinal domain, were much less curved than at present. Major transform faults The Carpathian fold belt retains lits general structural integrity along its nearly km long segment (West Carpathians and East Carpathians) between the Vienna Basin in the west, and the Moesian Platfonn in the east (Fig. 1). Rapid changes in tectonic style and tren ds, and sedimentary facies, appear at both terminations: at the West CarpathiansEastern Alps junction in the west, and at the East CarpathliansSouth Carpathians june tion in the east. These two junctions may correspond to palaeotransfonn faults, the Vienna Transfonn, and the Mure Transfonn, respectively (Birkenmajer, 1 985c, e). The Vienna and Mure transforms, as conservative structures of ocea nie bottom resulting from unequal oceanic rift expansion on both sides of the transfonns, would effeetively separate stretehes of oceanic crust of partly different age, and sedimentary basins superimposed upan either oceanic or upon attenuated continental crust. Rift relocation Taking into acoount the data from the East Carpathians where se veral stretehes of oceanictype erust progressively younger and younger toward the outside of the Carpathian belt have been recognized (see, e.g., Sandulescu, 1 983, 1 984; Siinduleseu et al., 1981; Bombiła & Savu, 1 985), it seems that oceanie rifting started dn the south about the Triassic Liassic boundary (), then it was relocated further north during the LiassicDogger times forming a new crust (), eventually it jumped again to the north at the JurassicCretaceous boundary () forming there the youngest oceanic erust of the Carpathian realm (Fig. 4). The above rift relocatlion, imposing a timerelated geosynclinal and orogenie polarity over the whole Carpathian domain, would correspond to the following oceaniccrust domains: () ApuseniTransylvanian domain in the east, propagating westward in the Pieniny Klippen Basin (central furrow); () Magura Trough domain, including the Poiana Botizei klippes in the east: either a separate rift or a northwardrelocated branch of en; () Outer Dacides domain (in the east), propagating as initial rift westward, in the Silesian Basin.

21 N NORTH EUROPEAN O U T ER 5 U B 5 1 LE51AN SLE SAN 5 U BMERGEO E L E VATEO R OGE R OGE : PLATFORM : 1 5KOLE B A5 1 N 1 : : : 1 T TJ 1 1 BA51 N Volcanism Marine deposits Mantle N N E R r D O MA N 5UBMA GURA 5 1 L E5 1 AN o \ i L\\. _ l T.r1"1 GO sa 1 00! k m '" i i l i i ', r===\ C A R PA T H A N BA51N M A G U R A BA51N?f ił1... ', CAR PATH AN P E N NV K L lppen BAS N CZO R SZT Y N SUBME RGEO R OG E : : C : Fz N Br P! 1 1 : ARC : / BAS \ol ( ) ) '7 \ s ii et al z H GHTAT R C, E L EVAT EO M A N N R O GE : :m:: 1 exot l c R OGE H DOMA N O u J1J O...,, D N o< en N "l O lzj tl: Si l'l Z E:: Continental c.rust Oceanic crust {@ M a l m/ Neoco m ian Upper Lassc / Dogger o Lower Liassic /Upper Trioss/c Fig. 4 Palinspastic reconstruction of the Carpathian basins along the KrakówZakopane geoltraverse. AptianAlbian stage. exten sion il Outer Carpathian domain, compression and crustal shortening starting in nner Carpathim domain (after Birken maj er, 1985c) oceanie rift; C Czorsztyn Ridge; Cz,, subsequent stages of oceanie crust formation due to northward relocation of Czertezik zone; N Niedziea zone; Br Branisko zone; P Pieniny zone; H Hallgovce zone...) " l'l

22 STAGES OF STRUCTURAL EVOLUTON OF THE PENNY Each relocation of oceanie rift outwards (l) would have left behind a stretch of oceanie crust of considerable (largely unknown) width. This stretch was then inactive (dormant) during the following goosynclinal expansion stage, with cha1acteristic deepwater sedimentation prevailing. Disturbances referrable to rift relocation and rift expansion were expressed as faulting, uplift and deposition of clastic (flysch) wedges along margins of continental crust slivers (microcontinents) affected. The latter microcontinents were separated from their parent European Platform by the mechanisms of rift relocation. Destructive plate boundaries There are only infrequent, slight evidences for appearance of destructive plate boundaries in the Carpathian domain prior to the Jurassic Cretaceous boundary hlmes. Basaltic and " trachytic " (andesitic) detritus (Siindulescu et al., 1981; Bombita & Savu, 1985) which appears in Oxfordian limestones of the Poiana Botizei klippes in Rumania (Grajcarek Unit), may be considered as an evidence of subduction of the Magura Trough oceanie crust under the Czorsztyn Ridge, and of formation of inihlal andesitic volcanic arc adjacent to this ridge. n the Pieniny Klippen Basin, a destructive plate boundary appeared for the first time at the JurassicCretacoous boundary. t was caused by subduction of the 1st crust from the central furrow under the overriding slab of the Andrusov Cordillera (Exotic Ridge). This subduction continued at slow rate into midcretaceous times, causing sedimentary breaks at the base of the Albian, the appearance of olistostromes and flysch deposits (AptianAlbian through Lower Turonian) and, finally, the northvergent nappe thrusting in the area to the south of the cordillera, in the Manin (s.1.), Hightatric, and Subtatric zones, in the succession. '1'here are no evidences for any active oceamc rift durtrtg midate l.retaceous time in either the Western or the Eastern Carpathians. The motoric cause for the Early through Late Cretaceous subduction in the West Carpathian domain could be a newlyformed fastexpanding oceanie ridge located to the south of the Gemerid zone: either in the Pannonian area, between Mecsek Mts and Biikk Mts, or in the Vardar zone of Dinarides. The remaining oceanie crust segments and became mobilized in West Carpathians during the Late Cretaceous (late Subhercynian to late Laramian) orogeny. t seems that a large part of the nd crust segment had not been subducted until the Miocene (Savian and Styrian) oontinentcontinent collision between the European Plate and the nner CarpathianPannonian Block (microcontinent). STAGES OF STRUCTURAL EVOLUTON OF THE PENNY KLPPEN BELT Nine distinctive stages of structural evolution of the Pieniny Klippen Belt have been distinguished. The most important ones have been illustrated in Figure 5.

23 N K L P PEN BELT BA SN s Mg : c :Cz: N : B, p H,, Mn E, K, sea Jevel +J lorl, km 50, M g sea ""6 ' CENOMANAN O',, <'//0" :.oo..s bl uesehist, metamorph,sm F:::::J ł upl;1t teetonie r transport elaslie transport./ eontinental crust.. T] manile m lange oceanit erust carbonales and radiolarian cher1s lysch molasse and wildllysch 1f orogenie plulonism + +/+ and volean;sm + + _ overthrus\. ""''\ and nappes pastorogenie plutons Fig. 5 Model of structural evolution of the Pieniny Klippen Be1t, central sector (after Birkenmajer, 1985b) Stratlgraphic successions and tectonic unlts: Mg Magura; G Grajcarek; C Czorsztyn; Cz Czertezlk; N Niedzlca; B Branisko; P Pieniny; H Hallgovce: E Exotic 'Andrusov Rldge) ; K Klape; Ma Manln; T Hightatrlc; ST Subtatric; PKB Pieniny Klppen Belt

24 STAGES OF STRUCTURAL EVOLUTON OF THE PENNY (A) nitial stage of basin formation The initial stage of basin formation was that of extensional faulting close to the TriassicJurassic boundary (EoCimmerian movements), and the ' resulting fragmentation of the Triassic carbonate platform. The inlitial depression of the Pieniny Klippen Basin thus formed, with its downthrown part later transformed into central furrow, and upthrown margins later transformed into the Czorsztyn Ridge and the Andrusov (Exotie) Ridge, respeetively. (B) nitial expansion stage The initial expansion stage is related to oeeanietype rifting and oceanfloor spreading. This is a hypothetical stage with respect to the majority of the Pieniny Klippen Basin, as Only indireet dnformation is available. t is assumed that Oceanie rift propagating westward from the Transylvanian domain split the downthrown part of the initial basin in two, ereatdng a relatively narrow zone of oceanie erust (crust ) at the TriassieJurassic boundary, and effeetively separated the Czorsztyn from the Andrusov ridges. A relocation of this rift to the north, and flormation of new oceanie erust (crust ) is suggested to have oeeurred during Late Liassic or even MidLate Jurassie times, to the north of the Czorsztyn Ridge. Sueh relocated rift, now situated within the Magura zone, would be responsible for separating the Czorsztyn Ridge from the Silesian Ridge (and its Maramure equivalents). (e) Pelagie stage The pelagie (preflysch) stage (sensu Aubouin, 1965) is very well marked in the development of pelagie Bositra ("Posidonia") shales, radiolaria cherts and bianconetype (cherty) ldmestones confined mainly to the central and northern furrows, and much less distinct in the southern furrow. The Czorsztyn Ridge was submerged for most Of its Mesozoic history, being the site of organogenie calcaroous seddmentation, with characteristic crinoid limestone, nodular limestone (ammonitico rosso) and lumachelle development, devoid Of radiolaria cherts. Numerous hiatuses and condensed ironmanganeserich residual beds Originated due to submarine dissolution of calcium carbonate, Extensional gravity faulting was marked especially at MidUpper Jurassie (MesoCimmerian) and Upper Jurassic Lower Cretaceous boundaries (NeoCimmerian). The NeoCimmerian movements we re particularly intense, eausing brecciation, fragmentation and resettling of older, al re ady diagenesized seddments, and formation Of horst andgraben structures. t is a good reason to believe that the NeoCimmerian phase of faul1ling was a direct response to initiation of subduction along the northern, active (leading) edge of the Andrusov Cordillera. The NeoOimmerian movements were manifested as sedimentary breaks (Berriasian Valanginian) in the transitional successions of the central furrow (Czertezik and Niedzica successions). n the Poiana Botizei klippes in Rumania (Grajcarek Unit: southem margin of the northem Magura furrow), redeposition tof mafie clasts noted in Malm limestones,